中国东部大陆边缘中生代晚期增生过程的数值模拟：以那丹哈达为例

陶建丽; 楼达; 戴黎明; 李三忠; 董昊; 马芳芳; 兰浩圆; 李法坤; 王亮亮; 刘泽

doi:10.16562/j.cnki.0256-1492.2019040101

中国东部大陆边缘中生代晚期增生过程的数值模拟：以那丹哈达为例

陶建丽^1,2,,
楼达³,
戴黎明^1,2, ,,
李三忠^1,2,
董昊^1,2,
马芳芳^1,2,
兰浩圆^1,2,
李法坤^1,2,
王亮亮^1,2,
刘泽^1,2

1.
海底科学与探测技术教育部重点实验室，中国海洋大学海洋地球科学学院，青岛 266100
2.
青岛海洋科学与技术国家实验室，海洋地质过程与环境功能实验室，青岛 266237
3.
中国石油大港油田公司，天津 300280

基金项目: 国家重点研发计划项目“多板块汇聚与晚中生代成矿大爆发的深部过程”(2017YFC0601401)、“华北古陆中新元古代原型盆地及差异改造”(2016YFC0601002)；国家自然科学基金重大研究计划“西太平洋地球系统多圈层相互作用”(91858215)

详细信息

作者简介:
陶建丽(1993—)，女，硕士生，从事地球动力学数值模拟研究，E-mail：ouctaojianli@faxmail.com

通讯作者:
戴黎明(1980—)，男，副教授，从事构造地质学及其数值模拟研究，E-mail：dlming@ouc.edu.cn

中图分类号: P736.15
计量
- 文章访问数: 2971
- HTML全文浏览量: 567
- PDF下载量: 45
出版历程
- 收稿日期: 2019-03-31
- 修回日期: 2019-04-15
- 网络出版日期: 2019-11-06
- 刊出日期: 2019-09-30

Numerical simulation of Late Mesozoic accretion process along the continental margin of East China: A case study of the Nadanhada Terrane

TAO Jianli^1,2,,
LOU Da³,
DAI Liming^1,2, ,,
LI Sanzhong^1,2,
DONG Hao^1,2,
MA Fangfang^1,2,
LAN Haoyuan^1,2,
LI Fakun^1,2,
WANG Liangliang^1,2,
LIU Ze^1,2

1.
Key Lab of Submarine Geosciences and Prospecting Techniques, MOE, Institute for Advanced Ocean Study, College of Marine Geosciences, Ocean University of China, Qingdao 266100, China
2.
Laboratory for Marine Mineral Resources, Qingdao National Laboratory for Marine Science and Technology, Qingdao 266237, China
3.
PetroChina Dagang Oilfield Company , Tianjin 300280, China

摘要

摘要: 许多现存造山带中均发现了洋岛玄武岩（OIB）和地幔柱型蛇绿岩记录，因此洋底高原增生是大陆生长的重要方式，但目前对控制洋底高原增生过程的机制仍不清楚。采用热-机械-岩石学模型数值模拟研究洋底高原的陆缘增生过程，结果显示洋底高原向大陆边缘增生具有3个控制因素：（1）减薄的大陆边缘；（2）海洋岩石圈中的“薄弱”层；（3）年轻的洋底高原。模拟结果与中国东北地区那丹哈达地体的野外构造解析结果和地球化学特征结合，揭示了洋底高原和东北亚大陆边缘的强烈挤压引起俯冲带的应变集中，产生与阿尔卑斯型褶皱相关的高角度逆冲断层和背冲断层，并伴随低级变质作用的构造折返过程。
- 洋底高原增生 /
- 数值模拟 /
- 构造折返 /
- 那丹哈达地体
Abstract: Accretion of oceanic plateau is an important process of continental growth, and is exemplified by the presence of oceanic island basalts (OIB) and plume-type ophiolites in many modern orogens. Oceanic plateau can also subduct along convergent margins, as revealed by seismic tomography. The mechanism controlling accretion or subduction of oceanic plateau remain unclear. In this paper, we investigate the accretion of oceanic plateaus at continental margins using a thermo-mechanical-petrological model of an ocean-continent convergent zone. The results of the models show three major factors for the accretion of the oceanic plateaus onto the continental margin: (1) thinned continental margin for the overriding plate, (2) " weak” layers in oceanic lithosphere and (3) young oceanic plateau. The results of the model are further compared with the field structural analysis and geochemical characteristics of the Nadanhada Terrane in Northeast China. It is revealed that the intense compression of the seamount and the continental margin of Northeast Asia results in strain concentration in the subduction zone, forming high-angle thrust faults and back thrusts associated with the Alpine-type folds, and structural exhumation of low-metamorphic rocks through thrust faults.
- oceanic plateaus accretion /
- numerical modelling /
- tectonic exhumation /
- Nadanhada Terrane

HTML全文

图 1 那丹哈达及周缘地体的构造格局（根据文献[15, 20]）

红框标注为那丹哈达地体。断裂编号：①依兰-伊通断裂，②敦化-密山断裂，③牡丹江断裂，④中锡霍特-阿林断裂

Figure 1. Tectonic units of the Nadanhada and surrounding terranes

NB is the abbreviation of the Nadanhada-Bikin Terrane. ①Yilan-Yitong Fault, ②Dunhua-Mishan Fault, ③Mudanjiang Fault, ④Sikhote-Alin Fault

下载: 全尺寸图片幻灯片

图 2 初始模型和边界条件

a. 是模型7的初始模型，图中尺度1 800 km×400 km为整个模型空间尺度（4 000 km×670 km）的局部。白色实线为等温线，单位是℃。b. 不同的颜色代表不同类型的岩石，岩性色标如下：1-空气；2-水；3和4-沉积物；5-大陆上地壳；6-大陆下地壳；7-大洋上地壳；8-大洋下地壳；9-洋底高原；10-岩石圈地幔；11-软流圈地幔；12-初始俯冲带（蛇纹石化地幔）；13和14-部分熔融沉积物（对应3和4）；15和16-部分熔融大陆地壳（对应5和6）；17和18-部分熔融大洋地壳（对应7和8）；19-部分熔融洋底高原；20-部分熔融橄榄岩地幔

Figure 2. Initial model and boundary conditions

a. Initial setup of Model 7. Enlargement (1 800 ×400 km) of the numerical box (4 000 ×670 km) is demonstrated. b. Colors indicate rock types, with the color grid as follows: 1-air; 2-water; 3 and 4-sediments; 5-upper continental crust; 6-lower continental crust; 7-upper oceanic crust; 8-lower oceanic crust; 9-oceanic plateau; 10-lithospheric mantle; 11-asthenosphere mantle; 12-initial subduction zone (weak zone mantle); 13 and 14-partially molten sediment(3 and 4); 15-16 partially molten continental crust (5 and 6); 17 and 18-partially molten oceanic crust (7 and 8); 19-partially molten oceanic plateau; and 20-partially molten peridotite

下载: 全尺寸图片幻灯片

图 3 小型洋底高原增生的构造演化过程及地形起伏（模型1正常陆缘）

a-d为物质场，上部为对应的地形线

Figure 3. Tectonic evolution process and topography changes during the small oceanic plateau accretion (Model 1 for normal continental margin)

a- d show composition fields and the corresponding form lines

下载: 全尺寸图片幻灯片

图 4 小型洋底高原增生的构造演化过程及地形起伏（模型6减薄陆缘以及蛇纹石层存在）

a-d为物质场，右侧为P-T-t轨迹，上部为对应的地形线。红色实线代表断层，蓝色F1、黑色F2分别代表第一、二期褶皱，蓝色和黑色虚线分别代表褶皱轴向

Figure 4. Tectonic evolution process and topography changes during the small oceanic plateau accretion (Model 6 for thinned continental margin and presence of serpentinized layers)

a-d show composition fields and the corresponding form lines. Colored squares on the snapshots are markers that refer to the diagrams with the P-T-t paths. Blue F1, black F2 display the first, second stages of regional folding, respectively. Blue and black dash lines show axial plane of folds

下载: 全尺寸图片幻灯片

图 5 小型洋底高原增生的构造演化过程及地形起伏（模型9减薄陆缘以及存在超铁镁质基底层）

a-d为物质场，上部为对应的地形线。红色实线代表断层，蓝色F1代表一期褶皱，蓝色代表褶皱轴向

Figure 5. Tectonic evolution process and topography changes during the small oceanic plateau accretion (Model 9 for thinned continental margin and presence of ultramafic layer)

a-d show composition fields and the corresponding form lines. F1 displays the stage of regional folding. Blue dash line shows axial plane of fold

下载: 全尺寸图片幻灯片

图 6 小型洋底高原增生的构造演化过程及地形起伏（模型7减薄陆缘以及新生的小型洋底高原）

a-d为物质场，右侧为P-T-t轨迹，上部为对应的地形线。红色实线代表断层，蓝色F1、黑色F2分别代表第一、二期褶皱，蓝色和黑色虚线分别代表褶皱轴向

Figure 6. Tectonic evolution process and topography changes during the small oceanic plateau subduction and accretion (Model 7 for thinned continental margin and the newly generated oceanic plateau)

a-d show composition fields and the corresponding form lines. Colored squares on the snapshots are markers that refer to the diagrams with the P-T-t paths. Blue F1, black F2 display the first and second stages of regional folding, respectively. Blue and black dash lines show axial plane of folds

下载: 全尺寸图片幻灯片

图 7 那丹哈达地体的增生样式

(a)那丹哈达北部野外素描图（根据文献[63]绘制），（b）那丹哈达地体东北N-W向逆冲推覆断层（GPS: E133°20′3.28″ N47°03′40.28″, H: 70 m）（改编自[64]）

Figure 7. Accretion model of the Nadanhada Terrane

(a) Schematic cross-section in the northern Nadanhada Terrane (modified after[63]) ，(b) The NW-dipping thrust faults in the eastern Nadanhada Terrane (GPS: E133°20′3.28″ N47°03′40.28″, H: 70 m) (modified after [64])

下载: 全尺寸图片幻灯片

表 1 模型中使用的黏滞性流变参数^{[28, 31-35]}

Table 1 Thermal and visco-plastic parameters used in the numerical models^{[28, 31-35]}

岩石类型	ρ₀ /(kg·m⁻³)	Cp /(J·kg⁻¹·K⁻¹)	K /(W·m⁻¹·K⁻¹)	Hr /(μW·m⁻³)	流变性质	η₀ /(Pa·s⁻¹)	E /(kJ·mol⁻¹)	V /(J·MPa⁻¹·mol⁻¹)	n	A_D /(MPa⁻ⁿ·s⁻¹)	C /MPa	sin （φ_eff）
沉积物	2 700	1 000	$0.64 + \dfrac{{1\;293}}{{T + 77}}$	2	湿石英岩	1.97E+17	154	0	2.3	3.20E-06	1	0.15
上陆壳	2 700	1 000	$0.64 + \dfrac{{1\;293}}{{T + 77}}$	1	湿石英岩	1.97E+19	154	0	2.3	3.20E-06	20	0.15
下陆壳	3 000	1 000	$1.18 + \dfrac{{807}}{{T + 77}}$	1	斜长石 An75	4.80E+22	238	0	3.2	3.30E-04	20	0.45
洋壳/洋底高原	3 000	1 000	$1.18 + \dfrac{{807}}{{T + 77}}$	0.25	斜长石 An75	4.80E+22	238	0	3.3	3.30E-04	20	0.45
新生成的洋底高原	2 900	1 000	$0.64 + \dfrac{{1\;293}}{{T + 77}}$	0.25	斜长石 An75	4.80E+20	238	0	3.3	3.30E-04	20	0.45
干地幔	3 300	1 000	$0.64 + \dfrac{{1\;293}}{{T + 77}}$	0.022	无水橄榄岩	3.98E+16	532	8	3.5	2.50E+04	40	0.6
含水地幔	3 200	1 000	$0.64 + \dfrac{{1\;293}}{{T + 77}}$	0.022	含水橄榄岩	5.01E+20	470	8	4	2.00E+03	1	0.06
蛇纹石化地幔	3 200	1 000	$0.64 + \dfrac{{1\;293}}{{T + 77}}$	0.022	蛇纹石	3.21E+36	8.9	3.2	3.8	1.97E-33	1	0.06
基性岩浆底侵作用	3 200	1 000	$0.64 + \dfrac{{1\;293}}{{T + 77}}$	3	单斜辉石	3.21E+36	670	0	2.7	1.56E-34	1	0.06
注：ρ₀为参考密度；C_p为比热容；k为导热系数；Hr为放射性热；C为内聚力；sin（φ_eff）为有效摩擦系数；η₀为参考黏滞参数；E为活化能；V为活化体积；n为应力指数；A_D为材料常数。

下载: 导出CSV

表 2 模型中部分熔融岩石的流变学参数^{[27, 31, 33]}

Table 2 Parameters of partially molten rocks in the numerical models^{[27, 31, 33]}

部分熔融岩石类型	ρ₀ /(kg·m⁻³)	Cp /(J· kg⁻¹·K⁻¹)	sin （φ_eff）	η₀ /(Pa·s⁻¹)	T_固相线 /K	T_液相线 /K	H_L /(kJ·kg⁻¹)	n	A_D /(MPa⁻ⁿ·s⁻¹)
部分熔融沉积物/上陆壳	2 500	1 500	0.06	5.00E+14	$ {899 + \dfrac{{179\;00}}{{P + 54}} + \dfrac{{202\;00}}{{\left( {P + 54} \right)^2}}\;\;P < 1\;200\;{\rm{MPa}}} $ $ {831 + 0.06P\;\;\;P > 1\;200\;{\rm{MPa}}} $	831+0.06P	300	1	2.00E-09
部分熔融下陆壳	2 500	1 500	0.06	5.00E+14	$ {973 - \dfrac{{70\;400}}{{P + 354}} + \dfrac{{778e5}}{{{{\left( {P + 354} \right)}^2}}}\;\;P < 1\;600\;{\rm{MPa}}} $$ {973 + 0.003\;5{{P}} + 0.000\;006\;2{{P^2}}\;\;\;P > 1\;600\;{\rm{MPa}}} $	1,423+0.105P	300	1	2.00E-09
部分熔融洋壳/洋底高原	2 900	1 500	0.06	1.00E+13	$ 973 - \dfrac{{70\;400}}{{P + 354}} + \dfrac{{778e5}}{{( {P + 354}) }^2}\;\;\;{{P}} < 1\;600\;{\rm{MPa}}$ $ {973 + 0.003\;5{{P}} + 0.000\;006\;2{{P^2}}\;\;\;{{P}} > 1\;600\;{\rm{MPa}}} $	1,423+0.105P	300	1	1.00E-07
注：ρ₀为熔融岩石的参考密度；C_p为熔融岩石的比热容；sin（φ_eff）为熔融岩石的有效摩擦系数；η₀为熔融岩石的有效摩擦系数；T_固相线为地壳的固相线温度；T_液相线为地壳的液相线温度；H_L为相变潜热；n为熔融岩石的应力指数；A_D为熔融岩石的材料常数。

下载: 导出CSV

表 3 模型条件设置

Table 3 Description of the numerical models used in this work

模型编号	减薄大陆边缘	蛇纹石化地幔	超铁镁质层基底	年轻的洋底高原	是否增生
1						图 3
2	√
3		√
4				√
5		√		√
6	√	√			√	图 4
7	√			√	√	图 2(a), 图 6
8			√
9	√		√		√	图 5
注：√ 代表符合条件。

下载: 导出CSV

参考文献(66)

[1]	Dobretsov N L, Buslov M M, Yu U. Fragments of oceanic islands in accretion-collision areas of Gorny Altai and Salair, southern Siberia, Russia: Early stages of continental crustal growth of the Siberian continent in Vendian-Early Cambrian time [J]. Journal of Asian Earth Sciences, 2004, 23(5): 673-690. doi: 10.1016/S1367-9120(03)00132-9
[2]	Tetreault J L, Buiter S J H. Future accreted terranes: a compilation of island arcs, oceanic plateaus, submarine ridges, seamounts, and continental fragments [J]. Solid Earth, 2014, 5(2): 1243-1275. doi: 10.5194/se-5-1243-2014
[3]	Liu L, Zhang J S. Differential contraction of subducted lithosphere layers generates deep earthquakes [J]. Earth and Planetary Science Letters, 2015, 421: 98-106. doi: 10.1016/j.jpgl.2015.03.053
[4]	Axen G J, Van Wijk J W, Currie C A. Basal continental mantle lithosphere displaced by flat-slab subduction [J]. Nature Geoscience, 2018, 11: 961-964. doi: 10.1038/s41561-018-0263-9
[5]	Wu F Y, Yang J H, Xu Y, et al. Destruction of the North China Craton in the Mesozoic [J]. Annual Review of Earth and Planetary Sciences, 2019.
[6]	Niu Y L, Liu Y, Shao F L, et al. Exotic origin of the Chinese continental shelf: new insights into the tectonic evolution of the western Pacific and eastern China since the Mesozoic [J]. Science Bulletin, 2015, 60(18): 1598-1616. doi: 10.1007/s11434-015-0891-z
[7]	Ding W W, Li J B, Wu Z C, et al. Late Mesozoic transition from Andean-type to Western pacific-type of the East China continental margin-Is the East China Sea basement an allochthonous terrain [J]. Geological Journal, 2017, 52(5): 1994-2002.
[8]	Huang H H, Wu Y M, Song X, et al. Joint Vp and Vs tomography of Taiwan: implications for subduction-collision orogeny [J]. Earth and Planetary Science Letters, 2014, 392: 177-191. doi: 10.1016/j.jpgl.2014.02.026
[9]	Zhou J B, Cao J L, Wilde S A, et al. Paleo-Pacific subduction-accretion: Evidence from Geochemical and U-Pb zircon dating of the Nadanhada accretionary complex, NE China [J]. Tectonics, 2014, 33(12): 2444-2466. doi: 10.1002/2014TC003637
[10]	Cloos M. Lithospheric buoyancy and collisional orogenesis: Subduction of oceanic plateaus, continental margins, island arcs, spreading ridges, and seamounts [J]. Geological Society of America Bulletin, 1993, 105(6): 715. doi: 10.1130/0016-7606(1993)105<0715:LBACOS>2.3.CO;2
[11]	Mason W G, Moresi L, Betts P G, et al. Three-dimensional numerical models of the influence of a buoyant oceanic plateau on subduction zones [J]. Tectonophysics, 2010, 483(1-2): 0-79.
[12]	Tetreault J L, Buiter S J H. Geodynamic models of terrane accretion: Testing the fate of island arcs, oceanic plateaus, and continental fragments in subduction zones [J]. Journal of Geophysical Research: Solid Earth, 2012, 117(B8).
[13]	Vogt K, Gerya T V. From oceanic plateaus to allochthonous terranes: numerical modelling [J]. Gondwana Research, 2014, 25(2): 494-508. doi: 10.1016/j.gr.2012.11.002
[14]	Yang S H, Li Z H, Gerya T, et al. Dynamics of terrane accretion during seaward continental drifting and oceanic subduction: Numerical modeling and implications for the Jurassic crustal growth of the Lhasa Terrane, Tibet [J]. Tectonophysics, 2018, 746: 212-228. doi: 10.1016/j.tecto.2017.07.018
[15]	李三忠, 张勇, 郭玲莉, 等. 那丹哈达地体及周缘中生代变形与增生造山过程[J]. 地学前缘, 2017, 24(4):200-212. [LI Sanzhong, ZHANG Yong, GUO Lingli, et al. Mesozoic deformation and accretionary orogenic processes around the Nadanhada Terrane [J]. Earth Science Frontiers, 2017, 24(4): 200-212.
[16]	Liu Y J, Li W, Feng Z, et al. A review of the Paleozoic tectonics in the eastern part of Central Asian Orogenic Belt [J]. Gondwana Research, 2017, 43: 123-148. doi: 10.1016/j.gr.2016.03.013
[17]	刘永江, 张兴洲, 金巍, 等. 东北地区晚古生代区域构造演化[J]. 中国地质, 2010, 37(04):943-951. [LIU Yongjiang, ZHANG Xingzhou, JIN Wei, et al. Paleozoic tectonic evolution in Northeast China [J]. Geology in China, 2010, 37(04): 943-951. doi: 10.3969/j.issn.1000-3657.2010.04.010
[18]	Ouyang H G, Mao J W, Santosh M, et al. Geodynamic setting of Mesozoic magmatism in NE China and surrounding regions: Perspectives from spatio-temporal distribution patterns of ore deposits [J]. Journal of Asian Earth Sciences, 2013, 78(12): 222-236.
[19]	Li S Z, Jahn B, Zhao S J, et al. Triassic southeastward subduction of North China Block to South China Block: Insights from new geological, geophysical and geochemical data [J]. Earth-Science Reviews, 2017, 166: 270-285. doi: 10.1016/j.earscirev.2017.01.009
[20]	Wu F Y, Yang J H, Lo C H, et al. The Heilongjiang Group: a Jurassic accretionary complex in the Jiamusi Massif at the western Pacific margin of northeastern China [J]. Island Arc, 2007, 16(1): 156-172. doi: 10.1111/j.1440-1738.2007.00564.x
[21]	Li J Y. Permian geodynamic setting of Northeast China and adjacent regions: closure of the Paleo-Asian Ocean and subduction of the Paleo-Pacific Plate [J]. Journal of Asian Earth Sciences, 2006, 26(3): 207-224.
[22]	Tang J, Xu W, Niu Y, et al. Geochronology and geochemistry of Late Cretaceous-Paleocene granitoids in the Sikhote-Alin Orogenic Belt: Petrogenesis and implications for the oblique subduction of the paleo-Pacific plate [J]. Lithos, 2016, 266: 202-212.
[23]	Kojima S. Mesozoic terrane accretion in Northeast China, Sikhote-Alin and Japan regions [J]. Palaeogeography Palaeoclimatology Palaeoecology, 1989, 69(3-4): 213-232.
[24]	Mizutani S, Kojima S, Shao J A, et al. Mesozoic radiolarians from the Nadanhada area, northeast China [J]. Proceedings of the Japan Academy Ser B Physical and Biological Sciences, 1986, 62(9): 337-340. doi: 10.2183/pjab.62.337
[25]	Gerya T V, Yuen D A. Charaterictics-based marker method with conservative finite-difference schemes for modeling geological flows with strongly variable transport properties [J]. Physics of the Earth and Planetary Interiors, 2003, 140(4): 293-318. doi: 10.1016/j.pepi.2003.09.006
[26]	Burg J P, Gerya T V. The role of viscous heating in Barrovian metamorphism of collisional orogens: thermomechanical models and application to the Lepontine Dome in the Central Alps [J]. Journal of Metamorphic Geology, 2005, 23(2): 21.
[27]	Gerya T V, 2010. Introduction to Numerical Geodynamic Modelling[M]. Cambridge University Press, New York.
[28]	Ranalli G. Rheology of the Earth: Deformation and Flow Processes in Geophysics and Geodynamics, 2nd ed[M]. Springer Science and Business Media, 1995.
[29]	Gerya T V, Yuen D A. Rayleigh-Taylor instabilities from hydration and melting propel ‘cold plumes’ at subduction zones [J]. Earth and Planetary Science Letters, 2003, 212(1): 47-62.
[30]	Gerya T V, Meilick F I. Geodynamic regimes of subduction under an active margin: effects of rheological weakening by fluids and melts [J]. Journal of Metamorphic Geology, 2011, 29(1): 7-31. doi: 10.1111/j.1525-1314.2010.00904.x
[31]	Bittner D, Schmeling H. Numerical Modelling of Melting Processes and Induced Diapirism In the Lower Crust [J]. Geophysical Journal International, 1995, 123(1): 59-70. doi: 10.1111/j.1365-246X.1995.tb06661.x
[32]	Clauser C, Huenges E. Thermal conductivity of rocks and Minerals[M]. Rock Physics and Phase Relations: A Handbook of Physical Constants. American Geophysical Union, 1995: 105-126.
[33]	Turcotte D, Schubert G. Geodynamics[M]. Cambridge university press, 2002: 1-456.
[34]	Hilairet N, Reynard B, Wang Y, et al. High-pressure creep of serpentine, interseismic deformation, and initiation of subduction [J]. Science, 2007, 318(5858).
[35]	Ranalli G, Murphy D C. Rheological stratification of the lithosphere [J]. Tectonophysics, 1987, 132(4): 281-295. doi: 10.1016/0040-1951(87)90348-9
[36]	刘静, 张金玉, 葛玉魁, 等. 构造地貌学: 构造-气候-地表过程相互作用的交叉研究[J]. 科学通报, 2018, 63:3070-3088. [LIU Jing, ZHANG Jinyu, GE Yukui, et al. Tectonic geomorphology: An interdisciplinary study of the interaction among tectonic climatic and surface processes [J]. Chin Sci Bull, 2018, 63: 3070-3088.
[37]	Mann P, Taira A. Global tectonic significance of the Solomon Islands and Ontong Java Plateau convergent zone [J]. Tectonophysics, 2004, 389(3-4): 0-190.
[38]	Shulgin A, Kopp H, Mueller C, et al. Structural architecture of oceanic plateau subduction offshore Eastern Java and the potential implications for geohazards [J]. Geophysical Journal International, 2011, 184(1): 12-28. doi: 10.1111/j.1365-246X.2010.04834.x
[39]	Dai L M, Li S Z, Li Z H, et al. Dynamic processes and mechanisms for collision to post﹐rogenic extension in the Western Dabie Orogen: Insights from numerical modeling [J]. Geological Journal, 2017, 52: 44-58. doi: 10.1002/gj.2993
[40]	Dai L M, Li S Z, Li Z H, et al. Dynamics of exhumation and deformation of HP-UHP orogens in double subduction-collision systems: Numerical modeling and implications for the Western Dabie Orogen [J]. Earth-Science Reviews, 2018, 182: 68-84. doi: 10.1016/j.earscirev.2018.05.005
[41]	Liu Z, Dai L M, Li S, et al. Mesozoic magmatic activity and tectonic evolution in the southern East China Sea Continental Shelf Basin: Thermo-mechanical modelling [J]. Geological Journal, 2018, 53: 240-251. doi: 10.1002/gj.3021
[42]	Liao J, Wang Q, Gerya T, et al. Modeling craton destruction by hydration‐induced weakening of the upper mantle [J]. Journal of Geophysical Research Solid Earth, 2017, 122(9): 7449-7466. doi: 10.1002/2017JB014157
[43]	Gerya T V, Perchuk L L, Burg J P, 20 08. Transient hot channels: perpetrating and regurgitating ultrahigh-pressure, high-temperature crust-mantle associations in collision belts [J]. Lithos, 2008, 103(1-2): 236-256. doi: 10.1016/j.lithos.2007.09.017
[44]	Li Z H, Liu M, Gerya T. Lithosphere delamination in continental collisional orogens: A systematic numerical study [J]. Journal of Geophysical Research Solid Earth, 2016, 121: 5186-5211. doi: 10.1002/2016JB013106
[45]	Clerc C, Jolivet L, Ringenbach J C. Ductile extensional shear zones in the lower crust of a passive margin [J]. Earth and Planetary Science Letters, 2015, 431: 1-7. doi: 10.1016/j.jpgl.2015.08.038
[46]	Ramos A, Fernández O, Torne M, et al. Crustal structure of the SW Iberian passive margin: The westernmost remnant of the Ligurian Tethys [J]. Tectonophysics, 2017, 705: 42-62. doi: 10.1016/j.tecto.2017.03.012
[47]	Ruiz M, Díaz J, Pedreira D, et al. Crustal structure of the North Iberian continental margin from seismic refraction/wide-angle reflection profiles [J]. Tectonophysics, 2017, 717: 65-82. doi: 10.1016/j.tecto.2017.07.008
[48]	Nair N, Pandey D K. Cenozoic sedimentation in the Mumbai Offshore Basin: Implications for tectonic evolution of the western continental margin of India [J]. Journal of Asian Earth Sciences, 2018, 152: 132-144. doi: 10.1016/j.jseaes.2017.11.037
[49]	Schubert G, Sandwell D. Crustal volumes of the continents and of oceanic and continental submarine plateaus [J]. Earth and Planetary Science Letters, 1989, 92(2): 234-246. doi: 10.1016/0012-821X(89)90049-6
[50]	Zagorevski A, Lissenberg C J, Van Staal C R. Dynamics of accretion of arc and backarc crust to continental margins: Inferences from the Annieopsquotch accretionary tract, Newfoundland Appalachians [J]. Tectonophysics, 2009, 479(1-2): 150-164. doi: 10.1016/j.tecto.2008.12.002
[51]	Johnson H P, Pruis M J. Fluxes of fluid and heat from the oceanic crustal reservoir [J]. Earth and Planetary Science Letters, 2003, 216(4): 0-574.
[52]	Vogt K, Gerya T. Deep plate serpentinization triggers skinning of subducting slabs [J]. Geology, 2014, 42(8): 723-726. doi: 10.1130/G35565.1
[53]	Campbell I H, Griffiths R W. Implications of mantle plume structure for the evolution of flood basalts [J]. Earth and Planetary Science Letters, 1990, 99(1): 79-93.
[54]	Davies G F. Topography: a robust constraint on mantle fluxes [J]. Chemical Geology, 1998, 145(3-4): 479-489. doi: 10.1016/S0009-2541(97)00156-3
[55]	Hill R I, Campbell I H, Davies G F, et al. Mantle Plumes and Continental Tectonics [J]. Science, 1992, 256(5054): 186-193. doi: 10.1126/science.256.5054.186
[56]	Niu Y, O'Hara M J, Pearce J A. Initiation of Subduction Zones as a Consequence of Lateral Compositional Buoyancy Contrast within the Lithosphere: a Petrological Perspective [J]. Journal of Petrology, 2003, 44(11): 764-778.
[57]	Burke K, Fox P J, Şengör A M C. Buoyant ocean floor and the evolution of the Caribbean [J]. Journal of Geophysical Research: Solid Earth, 1978, 83(B8).
[58]	Alsaad N, Van A R, Pranger A D, et al. Continental accretion: from oceanic plateaus to allochthonous terranes [J]. Science, 1981, 213: 47-54. doi: 10.1126/science.213.4503.47
[59]	Abbott D H, Drury R, Mooney W D. Continents as lithological icebergs: the importance of buoyant lithospheric roots [J]. Earth and Planetary Science Letters, 1997, 149(1-4): 0-27.
[60]	Mueller R F, Saxena S K. Metamorphic mineral facies[M]//Chemical Petrology. Springer, New York, NY, 1977: 181-198.
[61]	Gulick S P S, Bangs N L B, Shipley T H, et al. Three-dimensional architecture of the Nankai accretionary prism's imbricate thrust zone off Cape Muroto, Japan: prism reconstruction via en echelon thrust propagation [J]. Journal of Geophysical Research Solid Earth, 2004: 109.
[62]	Gutscher M A, Kukowski N, Malavieille J, et al. Episodic imbricatethrusting and underthrusting: analog experiments and mechanical analysis applied to the Alaskan accretionary wedge [J]. Journal of Geophysical Research Solid Earth, 1998, 103: 10161-10176. doi: 10.1029/97JB03541
[63]	万阔. 完达山地体构造特征、结构及增生过程[D]. 吉林大学, 2017 WAN Kuo. Tectonic features, structures and accretionary processes of the Wandashan Terrane, NE China[D]. Jilin University, 2017
[64]	兰浩圆. 华北东部及东北早中生代变形特征与构造演化[D]. 中国海洋大学, 2018 LAN Haoyuan. Early Mesozoic structural features and tectonic evolution in the eastern North China and Northeast China[D]. Ocean University of China, 2018
[65]	张魁武, 邵济安, 唐克东, 等. 黑龙江省东部跃进山群中绿片岩的地球化学特征及地质意义[J]. 岩石学报, 1997(02):43-47. [ZHANG Kuiwu, SHAO Jian, TANG Kedong, et al. The Geochemical Characteristics and the Geological Significance of Green-schists in Yuejinshan Group, East Heilongjiang Province, China [J]. Acta Petrologica Sinica, 1997(02): 43-47.
[66]	Sun M D, Xu Y G, Wilde S A, et al. Provenance of Cretaceous trench slope sediments from the Mesozoic Wandashan Orogen, NE China: Implications for determining ancient drainage systems and tectonics of the Paleo‐Pacific [J]. Tectonics, 2015, 34(6): 1269-1289. doi: 10.1002/2015TC003870